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Atoll Research Bulletin No. 322

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Atoll Research Bulletin No. 322 ATOLL RESEARCH BULLETIN NO. 322 ISSUED BY NATIONAL MUSEUM OF NATURAL HISTORY SMITHSONlAN INSTITUTION WASHINGTON, D.C., USA. October 1989 TECTONIC AND ENVIRONMENTAL HISTORIES IN THE PITCAIRN GROUP, PALAEOGENE TO PRESENT: CONSTRUCTIONS AND SPECULATIONS U T. SPENCER Interpretation of SEASAT geoid anomaly data and improved seafloor mapping of the south-central Pacific suggest a complex tectonic history for the islands of the Pitcairn ile Beno atoll formed at - 16m.y.BP at a 'hotspot' now south of the Easter micro- sequent progressive island development at Henderson (i3m.y.), Ducie (8m.y.) and Crough seamount (4m.y.) resulted from the lateral leakage of magma from the Beno lineation along an old fracture zone, itself originating during the Tertiary reorientation of the Pacific plate. At all four islands cessation of volcanism was followed by subsiden- and the development of a carbonate cap. By comparison, Pitcairn has been the product of recent (<lm.y.) volcanic activity along an independent, subparallel hotspot lineation. Nevertheless, this activity has interacted with the older island chain by transforming Henderson Island, through the process of lithospheric flexure, into an uplifted atoll with - 30m of relief. These tectonic processes have been accompanied by changes in sea level and oceanographic conditions. As the Holocene record shows, the deciphering of the sea level record at these islands is difficult; sea level change has been a response not only to glacio- eustatic processes but also to a range of isostatic, and possibly geoidal, effects. Although the Pitcairn group at -24OS occupies a marginal position for reef growth and development, reconstructions of paheoceanographic conditions for the Tertia and Quaternary suggest that the tropical water masses were largely unaffected by either changes in ocean circulation systems or climatic cooling and that water temperatures in the past have been very similar to those experienced at the present time. Until recently the tectonic and environmental history of the south-central Pacific has been poorly understood. Previous reconstructions of ocean basin and island histories have had to rely upon the relative paucity of information supplied fron infrequent and low density bathymetric traverses of research vessels. However, within the last decade the application of new remote-sensing technologies, improved mapping of the sea floor and the transfer of deep-drilling techniques refined in more accessible oceans has vastly expanded the volume of information available from even the remotest parts of the south Pacific. ............................................................................................................ I Department of Geography, University of Manchester, Manchester Mi3 9PL, UK; present address: Department of Geography, University of Cambridge, Cambridge CB2 3EN. Thus, for example, critical phases in the geological history of the oceanic lithosphere in this region took place in the early Miocene, a time period for which sea-floor magnetic anomalies are few and broadly separated in age, yielding more conjectural estimates for sea-floor spreading rates than at subsequent time periods. However, following the operation of the altimeter satellites GEOS-3 and more particularly SEASAT, variation in the height of the sea surface - the marine geoid - is now known throught the south Pacific (e.g. Sandwell 1984) to a height of accuracy of 10-30 cm and.a horizontal resolution of 10-50 km. Geoidal signals have a high level of correlation with sea-floor topography and have thus been used to discover previously undetected bathyrnetric features (e.g. Sabers et al. 1988), precise seamount geometry then being determined by multi-beam sonar mapping (e.g. Pontaise et al. 1986). As the following syntheses demonstrates, degree of detail of this kind has revolutionised the level of explanation of regional geodynamics and environmental change in the south- central Pacific. As a result, some preliminary reconstructions of tectonic and environmental histories for the Pitcairn group can be attempted. ibT RE-ORIENTMION OF THE PACIFIC PLAT At the beginning of the Palaeogene (65 million years B.P.) the prototypes for all the major oceans were already in existence. The Pacific was a multi-plate ocean, separated by subduction zone margins from the Asian and, in all probability, the Australian plate and bounded to the east by a complex series of mid-ocean ridges and triple junctions from the Farallon, Kula and Phoenix plates (Williams 1986; Figure 1). Although the Pacific Ocean was gradually reduced in size during the Palaeogene, with rates of subduction exceeding those of seafloor spreading, the Pacific plate itself increased in size at the expense of the plates on its western margin. The re-orientation of the plate, from a NNMr to WNW spreading direction at -42 million years B.P., preserved in the hot-spot traces of intra- plate islands and seamounts, most notably by the 'bend' in the Hawaiian Islands - mperor Seamounts chain, is well known, Of equal significance in the South Pacific, however, was the colli of the Pacific-Kula-Farallon boundary with the Farallon- Americas trench at -26 ion years B.P. This event stopped all seafloor spreading and subduction in this regio d initiated direct coupling between the Pacific and Americas plate. This fusion created a. major, progressive reorientat n of seafloor spreadirtg patterns and plate geometries as follows: i) -20 million years .P.: clockwise rotation of the southern portion of the Pacific-Farallon ridge and the development of the Galapagos rift; ii) -10 million years B.P.: break-up of ridge south of Baja California and ridge 'jumps' and iii) -5 million years B.P.: development, from the north, of the Gorda-Juan de Fuca-§an Andreas-Gulf of California spreading system with eastward ridge jump below Baja California and westward shift of the Galapagos triple junction (Herron 1972, Herron and Tucholke 1976, Handschumacher 1975). These adjustments were echoed in progressive plate re-orientations between 15-30° which have been fully documented by Okal and Cazenave (1985) using a full SEASAT dataset. At 40 million years B.P., spreading was taking place along the Mendoza and Roggeveen ridges (terminology : Mammerickx et al. 1980), offset 500 km by the transform fault of the Austral Fracture Zone (Figure 2a). Between 36 and 25 million years B.P. the Mendoza ridge propagated south, causing ridge re-orientation and the development of two fracture zones : FZ1, a re-orientation and re-located version of the Austral Fracture Zone and FZ2, dividing the northern and southern sections of the Roggeveen ridge (Figure 2b); Okal and Cazenave 1985, Sailor and Okal 1983, Okal and Bergeal 1983). Both these fracture zones are orientated N95OE, intermediate between the strike of the ancient Farallon ridge (N70°E) and the orientation of spreading of the present East Pacific rise (N1lOOE),are 400- 500 km in length and may be associated with comtemporary seismic activity (Figure 3; Okal and Cazenave 1985, Okal et al. 1980). The southern Roggeveen and the Mendoza ridges subsequently 'jumped' westwards at 20 and 18 million years B.P. respectively, completing the re-alignment of the Pacific plate boundary with a straightening of the spreading system, and perhaps providing the western boundaries of the present Easter micro-plate (Figure 2c) - f); Hey et al. 1985). STRUCTURAL TRENDS AND ISLAND AGES : SOUTHERN TUAMOTU ARCHIPELAGO AND PITCAIRN ISLAND. The islands of the Pitcairn Group- Ducie and Oeno atolls, Henderson Island and Pitcairn Island itself - lie between 23.S0S - 24.7OS and 124.7OW - 130.7OW. The islands are both widely spaced and isolated from their nearest neighbouring groups : Ducie atoll is 1000 km west of the Easter micro-plate; Oeno atoll is 450 km east of the Minerve reefs and the Gambier Islands (Figure 3). Henderson Island rises from water depths of -3,500 m: similarly, Pitcairn Island has been constructed from a sea floor at least 2,000 m and perhaps 3,500 m below the ocean surface. By comparision, Oeno atoll appears to rise from the southern side of a broad plateau at 1,600 m and Ducie atoll is probably not a simple feature (Mammerickx et al. 1975) but the surface expression of a complex collection of seamounts (Canadian Hydrographic Service 1982). Further to the east, clearly present in the SEASAT geoid but omitted from bathymetric charts, is a major structure topped by two seamounts reaching 1,000 m below present sea level at 25OS, 122.2OW and 24.g0S, 121.7OW; Okal (1984) has proposed that this feature be known as Crough Seamount. Geoidal signatures have revealed further seamounts around 25.6OS, 121.2OW and 26.2OS, 121.8OW (Okal and Cazenave 1985). Finally, the presence of several small seamounts near the East Pacific Rise is indicated by a cluster of geoidal anomalies. The regional synthesis of these recently-discovered submerged features indicates a much more complex and extensive island group lineation than has been apparent up to now from the disposition of islands above sea level. The alignment and spacing of the islands is strongly suggestive of an origin related. to a relatively-fixed melting anomaly, or 'hotspot', to the east of the islands and seamounts. Island chain hotspot traces should show a progressive increase in island age away from the hotspot itself in the direction of plate motion. However, given island morphologies in the Pitcairn Group, the only established dates for island genesis are from Pitcairn Island where potassium-argon dating of exposed volcanics has identified two phases of volcanism, at 0.46-0.63 and 0.76-0.93 million years B.P. The latter period. probably represents the main phase of island construction (Duncan et al. 1974). Basaltic lavas which form the islands of Mangareva, Aukena and Makapu, Gambier Islands, cooled between 5.2 and 7.2 million years B.P. (Brousse et al. 1972) and recovered basalts from Fangataufa atoll and Mururoa atoll have been dated to 7.1-9.1 million years B.P.
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